The record of the Paleocene-Eocene thermal maximum in the Ager Basin

21 Pages·2013·2.45 MB·English

Geologica Acta, Vol.11, Nº 4, December 2013, 421-441
DOI: 10.1344/105.000002061
Available online at www.geologica-acta.com
The record of the Paleocene-Eocene thermal maximum in the
Ager Basin (Central Pyrenees, Spain)
1 1,2 1,2
N. Minelli V. Manzi M. Roveri

1
Dipartimento di Fisica e Scienze della Terra Macedonio Melloni
Parco Area delle Scienze 157/A, 43100 Parma, Italy. Minelli E.mail: [email protected]
2 Alpine Laboratory of Palaeomagnetism (ALP)
Via Madonna dei Boschi 76, 12016 Peveragno (CN), Italy
ABSTRACT
The sedimentary record straddling the Paleocene-Eocene boundary in the Ager Basin (southern Central Pyrenees)
was investigated by combining facies analysis, sequence stratigraphy and stable isotope data, within an interval
characterized by a great variability of depositional environments. The occurrence of the Paleocene-Eocene thermal
maximum climatic anomaly is tentatively constrained by analogy with its stratigraphic range in the adjacent
Tremp-Graus Basin. The main body of the carbon isotope excursion associated with this thermal maximum may
be recorded by lacustrine carbonates characterized by a ~ -3‰ shift in δ13C with respect to analogous deposits of
Thanetian age. A similar shift is recorded between in situ and resedimented pedogenic carbonates, a feature that
suggests the partial erosion of the Paleocene-Eocene boundary in the Ager Basin.
KEYWORDS Paleocene-Eocene thermal maximum. Southern Central Pyrenees. Isotope geochemistry.
INTRODUCTION it along a continental-to-marine transect, i.e. from the
southern Central Pyrenees domain to the deep-marine
The study of the Paleocene-Eocene Thermal Maximum successions of the Basque-Cantabrian region. Schmitz
(PETM) was extended in recent years into the southern and Pujalte (2003) and Schmitz et al. (2001), pointed out
Central Pyrenees foreland basin, where the Paleocene- the regional-scale effects of the PETM, expressed by an
Eocene boundary issue was complicated by its proximity increase in land erosion and continental runoff during the
with a continental/marine facies boundary. Schmitz and isotope excursion, driven by a stronger seasonal character
Pujalte (2003) reported that the Carbon Isotope Excursion of the climate.
of the Paleocene-Eocene Thermal Maximum (PETM CIE)
was preserved within the continental Tremp Formation In this paper we describe for the first time the
(Fm.) (sensu Mey et al., 1968) of the Tremp-Graus Basin sedimentary record of the PETM in the Ager Basin, a
(provinces of Lleida and Huesca, Spain), and correlated narrow thrust-sheet-top basin located south of the Tremp-
421
N. Minelli et al. The PETM record in the Ager Basin
Graus Basin. The main aim of our work is to constrain 2002, with references therein) caused overthrusting of
the stratigraphic range of this thermal maximum in the the northern margin of the Ager Basin, so this sector is
Ager area and to establish a more precise correlation to presently exposed only in a small portion. To the south,
the Tremp-Graus Basin. These are key elements to discuss the Millà (SW) and St. Mamet (SE) anticlines outline an
the implications of this hyperthermal event for the regional irregular basin margin, with a large transversal structural
geological evolution and for a better understanding of its depression (Baronia Trough, Fig. 1C). This depression
impact on continental depositional systems. and its bounding highs were probably active since the
Paleocene, as inferred from differential subsidence patterns
The early Paleogene sedimentary successions of the in E-W transects (e.g. fig. 2 in Colombo and Cuevas, 1993;
Tremp-Graus and Ager basins are comparable in general fig. 3 in Rossi, 1997b).
litho- and physical-stratigraphic terms (Mutti et al.,
1988, 1994). The more or less marked differences in the The most continuous outcrops are present along the
distribution of sedimentary environments were mainly northern flanks of the St. Mamet and Millà anticlines and
controlled by the local paleotopography and the overall in the Baronia Trough; they consist of rocks ranging from
morphostructural setting; the latter is in large part related the Campanian to the Ypresian. During the late Paleocene
to the early evolution of the structural high that separates the Ager Basin was filled by a succession of continental,
them, the Montsec thrust; (Mutti et al., 1985; Mutti et mainly flood-plain to lacustrine deposits (Upper Tremp
al., 1988; Mutti et al., 1994; Rosell et al., 2001; López- Fm.), interfingering with shallow-marine calcarenites,
Martínez et al., 2006). For an integrated inter-basinal study, which record a number of successive transgressive events.
the chronostratigraphic correlation between the Tremp and The sea was located to the west, and flooded each time
Ager basins is of primary importance, given that there farther to the east, depicting an overall transgressive trend
is no physical continuity between their respective early (Rossi, 1997a, fig. 1).
Paleogene successions. This is particularly important within
the ~1000m-thick continental Tremp Fm. or Garumnian The most extensive transgressions occurred in the late
facies (sensu Rosell et al., 2001, with references therein), Thanetian and early Ypresian (Fig. 2; Ferrer et al., 1973;
of Maastrichtian to lower Ypresian age. Rossi, 1997b). These two events flooded the entire basin,
and the younger one caused the establishment of marine
The precise location of the PETM, within the conditions up to the middle-late Ypresian. The older
succession encompassing the interval between the late transgression (late Thanetian) was a short-lived event,
Thanetian (sensu Gradstein et al., 2004) and the Ypresian ended by a relative sea-level fall marked by an exposure
(Paleocene-Eocene boundary interval) in the Ager Basin, surface with paleokarst features (Rossi, 1997a; Rossi,
represents an even more challenging issue than in the 1997b) that can be easily followed throughout the southern
Tremp-Graus Basin, due to the greater variability of margin of the basin. The upper Thanetian and lower
sedimentary environments and lower outcrop quality. Ypresian marine deposits are separated by a continental
These two conditions hamper the reconstruction of a interval, which includes the Paleocene-Eocene boundary
continuous isotope record. However, the integration of interval in the Ager Basin.
facies and sequence-stratigraphic analysis with the isotope
data, and the comparison with the coeval interval in the The Paleocene-Eocene thermal maximum and the
Tremp-Graus Basin, allowed an isotope characterization of Paleocene-Eocene boundary in the southern Central
some distinctive lithological units, constraining the onset Pyrenees foreland basin
of the PETM CIE to a very narrow interval.
The PETM is a short-term episode of global warming
(Kennett and Stott, 1991), driven by a massive increase
GEOLOGICAL SETTING of atmospheric CO characterized by a very depleted
2
δ13C ratio (Carbon Isotope Excursion, CIE). The causes
The Ager Basin (Fig. 1B, C) is currently structured in of this phenomenon are still uncertain, but some global
an E-W trending, asymmetric syncline, the Ager Syncline and local consequences (involving environmental and
(Mutti et al., 1985; Mutti et al., 1994), bounded by the biotic changes), have been outlined with clarity because
Montsec thrust to the north and the inner anticlines of of the ease of recognition of the isotope signals (δ18O and
the Sierras Marginales to the south (Millà and St. Mamet δ13C) in sedimentary successions ranging from abyssal to
anticlines). The Montsec thrust separates the Ager Basin continental environments (e.g. Kennett and Stott, 1991;
from the Tremp-Graus Basin (Fig. 1B) and acted as a Koch et al., 1992).
topographic high at least since the Paleocene (Mutti
et al., 1985; Rosell et al., 2001; Muñoz, 2002). Later Apart from the paleoenvironmental implications of the
reactivations of this structure (Oligocene; cf. Muñoz, PETM, the isotope signal (particularly the CIE) constitutes
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N. Minelli et al. The PETM record in the Ager Basin
FIGURE 1 Geological setting of this study; A) geographic location of the study area; B) Schematic geological-structural map of the southern Central
Pyrenees (slightly modified after Mutti et al., 1988); the area occupied by the Ager and Tremp-Graus basins at the beginning of the Eocene are re-
presented in grey; C) geological map of the Ager Basin, based on the Mapa Geològic de Catalunya of the Institut Geològic de Catalunya (ICG), scale
1:250,000; D, E) detailed geological maps (based on ortophotomaps, scale 1:5,000) at the study sections; topography derived from the topographic
map of the Institut Cartografic de Catalunya (ICC), scale 1:5,000.
Geologica Acta, 11(4), 421-441 (2013) 423
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N. Minelli et al. The PETM record in the Ager Basin
a powerful correlation tool, allowing to trace a virtually
isochronous surface, and an unifying criterion for the
Paleocene/Eocene boundary (Aubry et al., 2007).
Tremp-Graus Basin
In the northern sector of the Tremp-Graus Basin,
Schmitz and Pujalte (2003) and Schmitz and Pujalte (2007)
localized the Paleocene-Eocene boundary within the upper
portion of the Tremp Fm. (Claret Fm., sensu Pujalte and
Schmitz, 2005) by recognizing the PETM isotope record
in paleosol carbonate nodules in a number of sections, thus
allowing to trace a continental-to-marine transect of the
PETM, i.e. from the southern Central Pyrenees foreland
basin to the basin plain deposits in the Basque-Cantabrian
domain (Fig. 3). In the Esplugafreda section (cf. Fig. 1B)
clay-mineral compositions show higher kaolinite content
within the syn-PETM paleosols, suggesting an increase
of land erosion during the climatic anomaly (Schmitz and
Pujalte, 2003). This was explained by the occurrence of a
seasonally humid climate, which contrasted with the arid
conditions typically observed during the Paleocene in this
Fully marine Evaporites
region.
Paleo-karst surface
Continental/Paralic
A striking feature related to the PETM onset is the
occurrence of a distinctive tabular conglomerate unit, the Magnetic polarity zones Shallow-benthic
zones
Claret conglomerate at the turning point between pre- and
syn-CIE δ13C values (this relationship was better defined FIGURE 2 Chronostratigraphic framework of the studied interval, in-
by organic matter δ13C by Domingo et al., 2009). Schmitz cluding the main lithostratigraphic units encountered in the Paleoce-
ne/Eocene transition in the Ager Basin. The ages of the sequence
and Pujalte (2003) interpreted the Claret conglomerate
boundaries are very approximate, since they are mainly bound to
as a fluvial deposit recording a major continental runoff benthic biozones.
increase (possibly enhanced by a relative sea-level fall)
related to the initial PETM. Evidence for syn-PETM above this sequence boundary, is a few-m-thick, very
increased continental runoff in the Pyrenean region was distinctive lithohorizon, which constitutes a basin wide
also provided by Storme et al. (2012) in the correlative keybed. To the east, the Claret conglomerate is overlain by
basin-plain succession of Zumaia (Basque Pyrenees). In a package of moderately pedogenized mudstones formed
the Tremp-Graus Basin, the PETM occurs within a small- during the PETM (yellow paleosols of Schmitz and Pujalte,
scale depositional sequence (the Serraduy sequence of 2003), which are capped by post-PETM evaporites. Above
Luterbacher et al., 1991; Fig. 2), which encompasses the the latter, a gradual transition from palustrine-lagoonal
transition from the Tremp Fm. to the overlying marine to fully marine deposits is observed, forming the classic
Ilerdian deposits. lower Ypresian transgressive systems tract of the Serraduy
Sequence. On the basis of Pujalte et al. (2009b) correlation,
In the area between the Isabena and Noguera Pallaresa they concluded that the whole package of the yellow
valleys, the basal sequence boundary of the Serraduy paleosols formed during a phase characterized by relative
sequence is represented by a discontinuous belt of base-level rise and transgressive conditions. Despite some
channelized sandstones and conglomerates (Fig. 3), locally uncertainties in the placement of the CIE top in the Campo
emphasized by a sharp change of paleosol color (from red section and the effect of local subsidence, the continental
to yellow). These deposits were interpreted as the early interval between the Claret conglomerate and the marine
fill of an incised valley (cf. Eichenseer and Luterbacher, flooding surface clearly thickens towards the east; this
1992; Baceta et al., 2011). West of the Isabena river, in is consistent with a gradual eastward transgression. The
the area of Campo (Figs. 1B; 3), this sequence boundary upper boundary of the Serraduy sequence (not treated in
is represented by a subaerial exposure surface with this paper) coincides with a reactivation of fluvial systems,
paleokarst features developed on upper Thanetian marine which built small deltaic complexes of lower Ypresian age
algal boundstones (e.g. Scheibner et al., 2007; Pujalte et (e.g. La Farga Fm. in Barberà et al., 1997; cf. Eichenseer
al., 2009a). The Claret conglomerate, located a few meters and Luterbacher, 1992).
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N. Minelli et al. The PETM record in the Ager Basin
The Serraduy sequence and its component systems et al., 2007; Westerhold et al., 2008). Since in the upper
tracts can be traced also in the southern margin of the Thanetian of the Ager Basin fluvial deposits are generally
Tremp-Graus Basin, including a finer-grained equivalent of poorly developed, their occurrence between the Thanetian
the Claret conglomerate (e.g. Eichenseer and Luterbacher, and Ypresian marine deposits suggests a direct relationship
1992; Waehry, 1999). with the period of enhanced fluvial discharge occurring
during the initial PETM.
Ager Basin
In the southern Ager Basin, the Paleocene-Eocene THE PALEOCENE-EOCENE BOUNDARY IN THE
boundary interval displays some similarities with the AGER BASIN
western portion of the Tremp-Graus Basin. In particular,
marine to coastal Thanetian deposits are topped in both Study locations
basins by a paleokarst, suggesting the occurrence of the
same sequence boundary, i.e. the lower boundary of the We studied the interval encompassing the Paleocene-
Serraduy Sequence (e.g. Rossi, 1997a). Also, the base of Eocene boundary in two sections located within the Baronia
the marine Ypresian (Alveolina limestones or Cadí Fm.) Trough (Fig. 1C): Altera W, located south of the village of La
roughly has the same age in both basins belonging to the Baronia de Sant Oïsme (Fig. 1D), largely exposed along the
Shallow-Benthic Zone 5 (SBZ 5; Serra-Kiel et al., 1998), C-13 roadcut; and Altera E, located along a path connecting the
which may represent a relatively short time interval, lasting C-13 road with the abandoned village of Peralba, on the eastern
300-400kyr. This value was obtained by Minelli (2012) side of the Altera hill (Fig. 1E). In the study area, beds dip
by integrating the PETM record (Pujalte et al., 2009b) roughly to the N, with an average inclination of 20°-25°, and
with the available chronostratigraphic constraints of the the main stratigraphic surfaces can be reliably traced for many
Tremp section (Fig. 2; Pascual et al., 1992; Serra-Kiel et kilometers. The studied interval also included the upper portion
al., 1994; Serra-Kiel et al., 1998; Waehry et al., 1999) and of the Thanetian, in order to collect isotope data from pre-PETM
with the recent early Paleogene age models (Westerhold strata. A description of the Paleocene-Eocene boundary interval
FIGURE 3 Simplified reconstruction of an E-W transect in the southern Pyrenean foreland during the Ypresian (modified from Schmitz and Pujalte,
2003, after Schmitz and Pujalte, 2007; Baceta et al., 2011), displaying the location of the main Paleocene-Eocene thermal maximum sections, and
the stratigraphic relationships of the thermal maximum with the units and surfaces discussed in the text. Notice that the range of this thermal maxi-
mum cannot be properly defined within the shallow-marine Ypresian carbonates (cf. Molina et al., 2003; Pujalte et al., 2009b), hampering a precise
reconstruction of the lateral relationships between shallow and deep-marine deposits of the Basque-Cantabrian region in this specific interval.
Geologica Acta, 11(4), 421-441 (2013) 425
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N. Minelli et al. The PETM record in the Ager Basin
was provided by Ullastre and Masriera (1998) in the eastern (facies wa and rare gr-tb and gr-cl; Fig. 5C) and subordinate
portion of the basin (Peralba section; Figs. 1C; 4). This section marls (facies m-gb). Vertical and lateral transitions (to
is very poorly exposed at present, particularly the finer-grained the E) to peritidal micrites (facies mi-wa; Fig. 5D) are
portions, and we have tentatively correlated our sections with it, observed. This stratigraphic organization depicts an overall
since it is the only high-resolution record of the PETM interval transgressive-regressive trend, as observed by Rossi (1997a).
in the Ager Basin available in the literature.
The mi-wa deposits are topped in both sections by a
Facies analysis and stratigraphy paleokarst, locally expressed by a decimetric layer of
micrite breccia (surface 2 – S2; Fig. 5D). Within the study
Facies analysis allowed to recognize 22 sedimentary facies area, the lateral continuity of the peritidal micrites just
(Table 1; Figs. 4; 5; 6) belonging to four main lithofacies: below S2 suggests a near-flat geometry for the paleokarst;
mudstones, carbonates, evaporites and siliciclastics. we were not able to recognize this surface in the Peralba
Sedimentary facies can be grouped into 9 facies associations section, and the proposed correlation with Ullastre and
representing 9 depositional elements and 5 continental to Masriera’s log (1998) is largely hypothetical.
coastal and shallow-marine depositional systems (Table
2). The succession can be subdivided into 6 informal units Unit B roughly coincides with the small-scale sequence
(labeled A to F from the bottom; Fig. 4); each of them is a 8 of Rossi (1997a), and encompasses the maximum
package of strata characterized by deposits formed in laterally flooding to highstand stage of the CTS.
related depositional systems. The surfaces separating these
units (Fig. 4) represent abrupt facies changes (marking Unit C
subaerial exposure and/or erosion and marine/lacustrine
flooding surfaces). As a consequence, these units can represent Unit C is continuously exposed only in the Altera E section,
systems tracts within depositional sequences developed on a where it is composed of a lower layer of yellow-mottled grey
decametric scale. Figure 4 displays the two logged sections mudstones (facies m-g), and an upper yellow paleosol (facies
and a possible correlation with the eastern Ager Basin. m-y). The two are separated by a sharp surface, outlined by a
thin micrite layer (facies mi-n; Fig. 5E). Centimetric yellowish-
Unit A white carbonate nodules are also present above and below this
surface. This is the only case of an evolved calcrete that we
This unit is made up of continental deposits underlying found in our study interval, possibly representing a Stage-IV
the late Thanetian transgression (unit B); its base has been calcrete (sensu Machette, 1985; cf. Alonso-Zarza and Wright,
placed at the top (surface 0 – S0) of a 1m-thick paleosol 2010). In the Altera W section, the mudstones of unit C are not
horizon (last red soil (LRS), Figs. 1D, E; 4; facies m-r) exposed; however, a poorly-preserved, ~50cm-thick nodular
representing a reliable local key horizon. Unit A is gypsum layer (facies e-n) topped by a dolomicrite horizon
dominated by paleosols with variable degrees of maturity (facies e-d), and an upper micrite layer (facies mi-l) have been
and/or humidity (mainly facies m-y and m-g; cf. Kraus and observed, clearly indicating the occurrence of a relative base-
Riggins, 2007), and includes a lenticular body composed of level rise and the development of a small and isolated water
lacustrine calcite-dominated carbonate deposits (facies m-l; body after the development of the S2 paleokarst.
Fig. 5A), and coastal saline lake deposits (facies e-m, e-l, e-n,
e-d; Fig. 5B) enclosed within grey continental mudstones This unit shows a variable thickness because of the
(facies m-g); thin organic matter-rich horizons (facies m-d) erosional character of its upper boundary (surface 3 –
are also found in association with e-d dolomicrites. S3); it is partially equivalent to the yellow to varicolored
marls/mudstones unit in the Peralba section (Ullastre
Unit A pertains to the late transgressive portion of the and Masriera, 1998); however, it is much thinner (~7m
Composite Thanetian sequence (CTS) of Rossi (1997a), at Altera E, ~1m at Altera W and ~15m at Peralba). This
and roughly overlaps with his small-scale depositional suggests that the lower part of the yellow to varicolored
sequence 7. It is topped by a marine flooding surface marls/mudstones at Peralba (Fig. 4) could actually be a
(surface 1 – S1) placed at the first occurrence of marine lateral equivalent of the regressive portion of unit B.
fossils (oysters) within a package of grey mudstones (m-g/
m-gb facies transition).This surface represents the base of Unit C records the E-W transition from a supratidal
the upper Thanetian marine carbonates of unit B. coastal environment to an alluvial one; its aggradational
stacking pattern indicates an accommodation space
Unit B increase, related to a relative sea-level rise, following the
phase of subaerial exposure and paleokarst development.
Unit B consists of marine deposits forming a ~25m-thick This suggests that unit C may already belong to the
package of subtidal to intertidal fine-grained calcarenites transgressive system tract of the Serraduy Sequence.
Geologica Acta, 11(4), 421-441 (2013) 426
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N. Minelli et al. The PETM record in the Ager Basin
sst-mvf
sst-mc
sst-vc
ch
cgl
m-r
m-b
m-y
m-g
m-d
m-gb
e-m e-l e-n
e-d
mi-n
mi-b
mi-wa
gr-cb
gr-tb
wa, (+ gr-cl)
wa
FIGURE 4 Correlated stratigraphic logs of the studied sections, including a tentative correlation with the Peralba section from Ullastre and Masriera
(1998); shaded areas represent the marine intervals.
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N. Minelli et al. The PETM record in the Ager Basin
TABLE 1 Sedimentary facies recognized in the studied interval
TABLE 1: Facies description and interpretation
Facies Lithology Interpretation
Mudstones
m-r red mudstones well-drained, mature paleosol
m-b brown mudstones relatively mature paleosol
m-y yellow mudstones poorly drained, incipient paleosol
m-g grey mudstones, locallyyellow-mottled mud flat/incipient paleosol
m-d dark mudstones swamp or lagoon
m-gb grey-blue mudstones with marine fossils lagoon/inner shelf
Carbonates
mi-n platy to nodular pedogenic micrite concretions calcrete
mi-l thin to medium-bedded micrites devoid of
lacustrine calcitic deposits
marine fossils
mi-wa laminated wackestones and micrites with
inter to supratidal deposits
miliolids
gr-tb massive, thin-bedded and relatively coarse-
storm deposits?
grained tabular grainstones
gr-cl poorly bioturbated calcarenites (fine-grained
sand flat/mixed flat transition
bimodal cross-laminated grainstones)
wa intensely bioturbated calcarenites (wackestones
inner shelf carbonates
and wackestones/packstones)
gr-cb large-scale cross-bedded coarse-grained
bioclastic tidal bar
grainstones with polymodal paleocurrents
Evaporites
grey mudstones with abundant gypsum nodules
e-m evaporitic mud flat
and veins
e-l lenticular laminated gypsum saline lake
e-n nodular gypsum early diagenetic productof faciese-l
e-d dolomicrites, locally with gypsum molds saline lake
Siliciclastics
cgl polymictic lenticular sandy orthoconglomerate with fluvial flood-related scouring and en-
resedimented pedogenic detritus (paleosol nodules, masse deposition (frictional freezing of
Microcodiumdebris, peloids) the coarse head of a bipartite sediment-
laden flow?) within a fluvial channel
ch chaotic deposit with sandy matrix and abundant frictional freezing of a debris flow
resedimented pedogenic (red mudstone clasts) and conveyed in a fluvial channel
palustrine materials (oncoids, stromatolites,
Microcodiumdebris, plant fragments)
sst-vc fan-shaped, scour-based, cross-bedded lenticular fluvial flood-related en-masse
very coarse to medium-grained pebbly sandstones, deposition, and partial winnowing within
with abundant mudstone clasts and plant a channel or at its mouth during lower-
fragments, sometimes bioturbated, high variability regime fluvial activity
in paleocurrent directions
sst-mc similar to sst-vcbut medium to coarse-grained, with mouth bar of a fluvial channel; minor
a less erosional or even transitional base (low- erosion related with end of flow
angle, thin-bedded bottomsets) and high-angle constriction
coarser foresets
sst-mvf medium to very fine-grained, tabular graded unconfined fluvial flood deposits
sandstones with planar to ripple- laminations and
hummocky cross-stratifications, with abundant
mudstone clasts and plant fragments, interbedded
with siltstones-mudstones
Unit D bedded mi-l beds occasionally encountered in the Altera
W section (this sub-unit may represent a transitional facies
This unit has a basal erosional surface (S3) truncating association between the siliciclastics of D1-D2 and the
unit C and consists of a ~35m-thick interval, organized in lacustrine carbonates of unit E). According to Ullastre and
a ~20m-thick lower sandstone package (sub-units D1 and Masriera (1998), D3 sub unit can be correlated with the
D2) and an upper, pelitic sub-unit (D3). The latter deposits horizon of brown (facies m-b), continental marls of the
are poorly exposed, with the exception of a few, very thin- Peralba section.
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N. Minelli et al. The PETM record in the Ager Basin
TABLE 2 Facies associations and depositional systems recognized associated with a change in paleocurrents suggesting a
in the studied interval
local shallowing of the depositional profile. Each coarse-
TABLE 2
grained, cross-bedded body is apparently characterized by
Facies Sedimentary Depositional a different direction of accretion. In one dihedral exposure,
associations environments systems bedding surfaces dip steeply to the south and more gently,
with a slightly tangential basal contact, to the west, while
m-r,m-b,
FP m-y,m-g, floodplain internal cross-laminations are dominantly west-trending,
mi-n alluvial plain apparently indicating a component of lateral accretion.
FC cgl,ch, fluvial channel
sst-mvf
The finer-grained sub-unit D2 is entirely exposed only
frontal
D sst-mc, river delta? in the Altera W section, although fine-grained tabular
sst-mvf splay/delta
beds can be encountered also to the east, indicating that
carbonate lake the two sub-units are laterally continuous for at least
CL mi-l,m-g
(freshwater) coastal lake some kilometers. In the Altera W section, these beds are
represented by medium- to very fine-grained sandstones
SL e-m,e-n, salina lake
e-l,e-d (facies sst-mvf; Fig. 6F). Moving slightly to the southeast
MF m-g,mi-wm mud flat inter to supra- from the section, a couple of small cross-bedded sandstone
carbonate tidal low- bars (facies sst-mc with transitional base; Fig. 6E) are
CB mi-wm, beach energy present at two different levels, suggesting the occurrence
gr-cl,gr-tb of lateral facies transitions between the cross-bedded and
(peritidal) shoreline
tabular facies. This may be supported by the paleocurrent
L m-d,m-gb, lagoon directions in the Altera W section, which display a general
wa,gr-tb
carbonate shelf northern or north-western attitude.
S gr-cb,gr-tb,
m-gb shelf
We infer that facies sst-vc, sst-mc and sst-mvf represent
a facies tract from fluvial channels to frontal splay (sensu
Dreyer, 1993)/sheetflood deposits, altogether stacked in a
The sandstone package is composed of coarse-grained, backstepping pattern from D1 to D2. Facies sst-mc represents
poorly sorted, lenticular and cross-bedded strata (facies the transition from confined (facies sst-vc) to unconfined
sst-vc, sst-mc; Fig. 6A, B) and finer-grained, relatively (facies sst-mvf) conditions, i.e a mouth-bar deposit. The
better sorted tabular beds (facies sst-mvf; Fig. 6F). The scarcity of pedogenic features in the sst-mc deposits (only
lenticular sandstone bodies are mainly concentrated in the observed in the sub-unit D1 in the Altera E section), and their
lower portion (sub-unit D1), where they are associated with absence in the sst-mvf beds, may imply the occurrence of
basal massive or crudely cross-bedded orthoconglomerates a relatively permanent water body to the north of the study
(facies cgl, only occurring in the Altera W section; Fig. locations, thus suggesting a deltaic origin of these deposits.
6A, B, C), characterized by abundant reworked pedogenic
material (reworked calcrete nodules and Microcodium Apart from the aforementioned continental carbonate
debris). A chaotic deposit (facies ch; Fig. 6B) was found detritus (which is likely to represent coeval or slightly
within sub-unit D1, similarly featuring abundant continental younger reworked material), the sandstones and
carbonate detritus (folded and convolute oncoids and conglomerates bear an abundant detrital carbonate
stromatolitic matter), chunks of m-r paleosols squeezed component and a subordinate siliciclastic one (both quartz
between the more competent blocks, and a prevalently and lithic detritus), i.e. they are substantially similar in
sandy matrix. This suggests deposition from subaerial composition to the Thanetian fluvial sandstones of the
debris flows, collecting detritus from both emerged areas Upper Tremp Fm. (e.g. Rossi, 1997b).
(paleosols) and ponds (the carbonate material), and finally
convoyed within fluvial channels. Unit D belongs to the Transgressive Systems Tract
(TST) of the Serraduy sequence. We interpret the erosional
In the Altera E section, the base of sub-unit D1 is features associated with sub-unit D1, rather than indicators
represented by a couplet of cross-laminated sandstone of falling relative base-level, as related with the intensity of
beds, characterized by a large amount of mudstone clasts, the flooding processes (see Discussion).
truncated by large, coarse-grained cross-bedded sandstone
bars (facies sst-mc with erosional base; Fig. 6D) with Unit E
internal cross-laminations (mainly climbing dunes),
large mudstone clasts and small wooden logs. The better Unit E is subdivided in two main packages of thin-
exposed body shows internal scours in its upper portion, bedded micrites, summing up for a total thickness of ~20m.
Geologica Acta, 11(4), 421-441 (2013) 429
DOI: 10.1344/105.000002061
N. Minelli et al. The PETM record in the Ager Basin
mi-l
S0
m-g
e-n
m-r m-y e-d
(paleokarst)
gr-cl
m-gb
wa
mi-wa
m-gb wa
S1
(marimn-eg flooding surface)
e-d
Incipient paleosol
(m-y)
mi-wa wa m-gb
m-d/m-gb
S(m5arine flooding surface)
m-g
Mud flat with
incipient pedogenic
features(m-g) mi-l
FIGURE 5 Carbonate, mudstone and evaporitic facies recognized in the study area (see description in the text). A) Unit A (base of the studied in-
terval), paleosols and lacustrine carbonates; B) Unit A, saline lake (evaporites and associated dolomicritic layer); C) Unit B, marine calcarenites;
D) Unit B, peritidal micrites and paleo karst; E) Unit C, calcrete nodules (circled; facies mi-n); F) Units E and F, lacustrine to sabkha and marine
deposits. Pictures A, B, C, F) Altera W section (C-13 roadcut); D, E) Altera E section. Hammer for scale in B and E is 33cm long; the Jacob Staff in
d is subdivided in 10cm segments; rulers in A, C, F are referred to the foreground outcrop surface. m-r: red paleosols; m-y: yellow paleosol; m-g:
grey paleosol; m-gb: marine mudstone; m-d: OM-rich mudstone; mi-l: lacustrine micrites; mi-wa: peritidal micrites; e-d: salina lake dolomicrite; e-n:
salina-lake, nodular gypsum; wa: subtidal, fine-grained calcarenites; gr-cl: intertidal laminated calcarenites; gr-cb: bioclastic tidal bars.
Geologica Acta, 11(4), 421-441 (2013) 430
DOI: 10.1344/105.000002061